Neptunian Dykes Penetrating the Lower Jurassic Dudziniec Formation in the Autochthonous High-Tatric Succession, Tatra Mountains, Western Carpathians, Poland

Acta Geologica Polonica, Vol. 68 (2018), No. 4, pp. 555–570 DOI: 10.1515/agp-2018-0013

Neptunian dykes penetrating the Lower Jurassic Dudziniec Formation in the autochthonous High-Tatric succession, Tatra Mountains, Western Carpathians, Poland

PIOTR ŁUCZYŃSKI and ANNA JEZIERSKA

Faculty of Geology, University of Warsaw, Żwirki i Wigury 93, PL-02-089 Warszawa, Poland. E-mails: [email protected]; [email protected]

ABSTRACT:

Łuczyński, P. and Jezierska, A. 2018. Neptunian dykes penetrating the Lower Jurassic Dudziniec Formation in the autochthonous High-Tatric succession, Tatra Mountains, Western Carpathians, Poland. Acta Geologica Polonica, 68 (4), 555–570. Warszawa.

The Lower Jurassic to Aalenian carbonate-clastic Dudziniec Formation exposed in the autochthonous unit of the Tatra Mountains (Kościeliska Valley) hosts neptunian dykes filled with various deposits. The development of the fissures took place in multiple stages, with the same fractures opening several times, as is indicated by their architecture, occurrence of internal breccias and arrangement of the infilling sediments. Various types of internal deposits were derived in a different manner and from different sources. Fine carbonate sediments, represented by variously coloured pelitic limestones, calcilutites and fine calcarenites, most probably come from uplifted and corroded carbonate massifs (possibly from the allochthonous units of the High-Tatric succession). Products of weathering, both in dissolved form and as small particles, were washed into the sedimentary basin of the autochthonous unit, and redeposited within the dykes. The sandy varieties of the infillings, represented by red, ferruginous calcareous sandstones, come directly from the host rocks or from loose sediments present on the sea bottom at the time of fracturing. The most probable age of the infilling sediments is Sinemurian to Pliensbachian. The occurrence of dykes of this age is yet another feature confirming that the sedimentary development of the Lower Jurassic sandy-carbonate facies in the autochthonous unit was strongly influenced by synsedimentary tectonic activity, such as block-faulting.

Key words: Neptunian dykes; Dudziniec Formation; Lower Jurassic; High-Tatric succession; Tatra Mountains.

INTRODUCTION mal lithostratigraphic division of the Jurassic of the Tatra Mountains (Lefeld et al. 1985), are referred The very first scientific interests of the late to as the Dudziniec Formation. Originally, as a stu- Professor Andrzej Radwański, marking the onset of dent of petrology, Prof. Radwański focused on the his splendid academic carrier, concentrated on topics petrography of the Lower Jurassic carbonate-clastic strictly connected with the scope of this paper. His sediments (Radwański 1959a). However, already at Master of Science thesis, prepared at the Faculty of that time his later devotion to the studies of dynamic Geology, University of Warsaw, was devoted to the processes and to sedimentology found its reflection studies of the High-Tatric Lower Jurassic (so-called in the published interpretation of littoral structures Liassic) deposits in the Chochołowska and Kościeliska from the base of the Jurassic, exposed in the Smytnia valleys, which today, after the introduction of a for- Valley (Radwański 1959b). He described a cliff struc- 556 PIOTR ŁUCZYŃSKI AND ANNA JEZIERSKA

Text-fig. 1. Geographic location of the study area. A – position of the Tatra Mountains in the Carpathians; B – structural map of the western part of the Polish section of the Tatra Massif ture that developed as a result of abrasion, which took sif is composed of a Variscan crystalline core and a place during the Early Jurassic sea transgression, as Permo-Mesozoic sedimentary cover, which due to the well as clastic dykes and veins that penetrate the top- tilting of the whole structure is exposed mainly on its most part of the Triassic, and which are filled with northern slopes. The sedimentary rocks represent two Lower Jurassic material. This description of fissures major successions (or series) differing in their facies remains, up to date, the only thorough investigation development and completeness – High-Tatric and Sub- of sedimentary dykes filled with sediments of the Tatric (Text-fig. 1B). The High-Tatric succession, ex- Dudziniec Formation reported from the High-Tatric posed in the topographically higher parts of the moun- succession of the Tatra Mountains. In the present pa- tains, is of both autochthonous and allochthonous per neptunian dykes are described that are developed character, and is represented mainly by shallow-water within the Dudziniec Formation, therefore higher in deposits with numerous stratigraphic gaps, whereas the lithological succession than those presented by the Sub-Tatric succession, preserved as nappes, is de- Radwański (1959a, b), but most probably also hosting veloped mainly in deeper facies and is more complete. sediments derived from the Lower Jurassic. These series correspond respectively to the Tatric Unit Professor Radwański continued his intensive (High-Tatric) and to the Fatric and Hronic units (Sub- works in the Tatra Mountains until his PhD in 1964, Tatric), referred to as major palaeogeographical units the thesis of which was devoted to the petrogra- of the CWC (Andrusov et al. 1973; Kotański 1979). phy and sedimentology of the High-Tatric Rhaetic The High-Tatric succession consists of three major (Radwański 1968). Unfortunately, later during his tectonic units – the autochthonous Kominy Tylkowe career, he switched to other topics and areas, stating Unit and the allochthonous (foldic) Czerwone Wierchy that “he will never come back to work in this cursed and Giewont units (Text-fig. 1B). The autochthonous mountain range where it always rains”. Time proved unit embraces also the so-called parautochthonous that he kept his promise. folds, with the sediments detached from the basement and moved on small distances, but palaeogeographi- cally still representing the same area. The foldic units GEOLOGICAL SETTING are overthrusted northwards to form the High-Tatric nappes (Jurewicz 2005, 2012), and in terms of pa- The Tatra Mountains are located in the Central laeogeography represent areas located south of the Western Carpathians (CWC) (Text-fig. 1A). The mas- autochthonous domain. NEPTUNIAN DYKES IN THE DUDZINIEC FORMATION, POLISH TATRA MOUNTAINS 557

Text-fig. 2. Simplified stratigraphic succession of the High-Tatric series (after Uchman 2014, modified)

The autochthonous unit represents the most mations are usually laterally discontinuous and are complete succession of the High-Tatric succession, preserved as lenticular bodies. Commonly the only whereas the parautochthonous folds and the alloch- indication of the deposition of sediments of particu- thonous units are less complete and contain large lar formations in a given area is their occurrence in stratigraphic gaps (Text-fig. 2). The most important neptunian dykes (Łuczyński 2001a, 2002). Based on difference is the occurrence of the Lower Jurassic the spatial relations between particular Jurassic litho- Dudziniec Formation in the autochthonous series, and somes, and on the occurrence of stratigraphic gaps its absence elsewhere. In the Czerwone Wierchy and between particular units, four main types of Jurassic Giewont units, the Triassic is directly overlain by the unconformities have been discerned in the High- Smolegowa (Bajocian; white crinoidal limestones), Tatric succession (Jezierska and Łuczyński 2016). In the Krupianka (Bathonian; mainly red crinoidal stratigraphical order these are: base of the Dudziniec limestones) or even the Raptawicka Turnia (starting Formation (erosional unconformity), base of the with Callovian; wavy bedded limestones) formations. Smolegowa Formation (paraconformity), base of the The Smolegowa and particularly the Krupianka for- Krupianka Formation (erosional unconformity) and 558 PIOTR ŁUCZYŃSKI AND ANNA JEZIERSKA

Text-fig. 3. Subdivision of the Dudziniec Formation (after Lefeld et al. 1985, modified)

base of the Raptawicka Turnia Formation (drowning – thin to medium-bedded, grey to black encrinites unconformity). Recurring episodes of erosion modi- with an admixture of quartz, and Triassic dolomites, fied the previously developed unconformity surfaces, alternating with spiculites, and (vi) Kominy Dudowe which resulted in the complex architecture of the Sandstone Member – medium-bedded, light-grey, Triassic/Jurassic contact, as well as between particu- pinkish-grey and yellowish conglomeratic-quartz- lar Jurassic lithosomes. Neptunian dykes filled with itic sandstones, calcareous in places. Generally, the various Jurassic sediments usually penetrate down- Dudziniec Formation is represented by shallower, wards from these unconformity surfaces. more proximal and more coarse-grained sandy-cri- The Dudziniec Formation, hosting the dykes noidal facies in the eastern area of its exposures described in this paper, occurs only in the Kominy (Kościeliska Valley; Staśkiewicz 2015; Jezierska et Tylkowe Unit and is developed in a wide range of al. 2016), and by deeper, more distal and finer facies sandy-carbonate facies. The Lower Jurassic lime- with spiculites on the west (Chochołowska Valley; stone and sandstone sequences of the High-Tatric K. Wójcik 1979, 1981). succession were described among others by Horwitz and Rabowski (1922), Siemiradzki (1923), Rabowski (1954, 1959), Kotański (1959), Radwański (1959a), JURASSIC NEPTUNIAN DYKES IN THE HIGH- Z. Wójcik (1959), K. Wójcik (1979, 1981) and Jezier- TATRIC SERIES OF THE TATRA MOUNTAINS ska et al. (2016). The detrital material contains quartz grains, carbonate lithoclasts and bioclasts (bivalves, The occurrence of dykes filled with sediments of- crinoids, brachiopods and belemnites). Based on ten provides a lot of valuable data on the developmental the belemnite and brachiopod faunas, the age of history and palaeogeography of the studied areas (e.g., the formation has been determined as Sinemurian− Lehner 1991; Winterer and Sarti 1994; Matyszkiewicz Aalenian (Horwitz and Rabowski 1922; Lefeld et al. et al. 2016) and yields unique stratigraphic and palae- 1985). Several members or beds are distinguished ontological information (Wendt 1971, 2017; Aubrecht within the formation (Lefeld et al. 1985; Text-fig. and Kozur 1995; Schlögl et al. 2009). Commonly the 3): (i) Kopieniec Starorobociański Bed – thin to me- infillings of dykes are the only preserved deposits dium-bedded, grey, dark-grey or blue-grey sandy representing particular stages of the given area’s de- limestones, (ii) Kobyla Głowa Limestone Member velopment (Jenkyns 1971; Jones 1992). Also in the – medium-bedded, dark-grey encrinites with small High-Tatric area, in the normal stratigraphic succes- amounts of clastic admixture, (iii) Kobylarka sion, counterparts of dyke infillings are preserved Lime stone Member – massive grey encrinites, (iv) usually only locally in the form of laterally discontin- Smytnia Limestone Member – poorly bedded grey to uous lenticular bodies, mostly as a result of Bajocian, dark-grey and black limestones containing brachio- Bathonian and post-Bathonian erosion. The Jurassic pods and bivalves, (v) Iwanówka Limestone Member neptunian dykes described so far from the High-Tatric NEPTUNIAN DYKES IN THE DUDZINIEC FORMATION, POLISH TATRA MOUNTAINS 559 area are summarised here in order to give a general ternal structure and architecture of neptunian dykes, overview and as material for comparison. particularly those running horizontally. Systems of The most common and best recognised Jurassic dykes belonging to Group II penetrate the substrate neptunian dykes in the High-Tatric succession are to greater depths, well exceeding 150 m. They com- those filled with Bajocian Smolegowa limestones and monly find their way along the heterogeneities of the Bathonian Krupianka limestones (Kotański 1959; host-rock and tend to run along bedding planes. Rabowski 1959; Wieczorek 2000; Łuczyński 2001a). The orientation, shapes and sizes of the dykes of Dykes of this age are present in all High-Tatric tec- Group I, as well as their relation to the host-rocks, in- tonic units. In the Czerwone Wierchy and Giewont dicate the solely mechanical nature of their initiation units, they penetrate solely the Triassic (Anisian and development processes. In contrast to that, in the limestones and dolomites). In the parautochthonous case of the dykes of Group II, chemical erosion, pos- folds (Rzędy pod Ciemniakiem) and in parts of the sibly also in subaerial conditions, played an important autochthonous unit (Chochołowska Valley) the dykes role. Short vertical dykes were filled by rapid injection cut also the Dudziniec Formation, mainly its top- of loose material deposited on the sea bottom into most part (Bagiński 1985; Łuczyński 2001a; Jezierski fissures opening in a hard brittle substrate (mainly in 2014). However, Wieczorek (2000, his fig. 4) men- the Bajocian) or were buried by migrating dunes of tions also dykes penetrating the lower parts of the crinoidal sand (mainly in the Bathonian). The occur- Dudziniec Formation, as well as the Lower Jurassic rence of fine unfossilliferous material (red micrite) of the Sub-Tatric succession. in the more remote parts of the vast dyke systems of The periods of formation of neptunian dykes Group II is a result of sieving. Many systems of dykes filled with Middle Jurassic deposits mark episodes show evidence of a multiphase history, during which of intensive substrate fracturing, most probably asso- the episodes of their infilling were separated by the ciated with extensional tectonic movements. The oc- development of ferruginous coats on the walls and by currence of dykes in the lower part of the Dudziniec precipitation of calcite cements in the voids. Formation and probably filled with Lower Jurassic Dykes filled with sediments that penetrate the material, described in this paper, may indicate that Dudziniec Formation have been described so far similar processes took place already in the Early only from its topmost part, mainly from the Rzędy Jurassic. Synsedimentary tectonics influenced the pod Ciemniakiem area in the parautochthonous folds sedimentary development of the High-Tatric domain (Bagiński 1985). In terms of their architecture they also in the Early Jurassic (Jezierska et al. 2016). belong to the Group I described above; however, Two main categories of systems of neptunian apart from being filled with crinoidal material and dykes filled with Middle Jurassic deposits and pen- red micrite they contain also yellow sandy limestones etrating the Triassic limestones and dolomites have resembling those of Lower Jurassic deposits. The na- been distinguished (for details see Łuczyński 2001a). ture of these sediments and the relation of the fissures Group I embraces dykes with sharp-edged walls and to the top of the Dudziniec Formation remains, how- predominantly vertical structures, whereas Group II ever, still dubious and requires further investigation. consists of dykes with smooth walls and running pre- Dykes filled with Lower Jurassic deposits and dominantly horizontally. Systems belonging to Group penetrating the Triassic have been described by I are mostly filled with white and red crinoidal lime- Radwański (1959b) from the Smytnia Valley (a rami- stones, of the Smolegowa and Krupianka formations fication of the Kościeliska Valley). The dykes accom- respectively, and by calcite cements. In some places, pany a cliff structure developed in the Norian sub- the Triassic substrate is so densely penetrated by frac- strate and penetrate down from an abrasion surface tures filled by sediments and cements as to form in to a depth of 11 m. They are filled mainly with cal- situ internal breccias. The dykes of this group pene- careous quartz-dolomite sandstones, identical to the trate the substrate to depths not exceeding a dozen or overlying Lower Jurassic deposits, and with yellow so metres. Group II embraces structures filled with dolomitic marls in more remote parts of the systems, pure red micrite and those associated with pressure often terminating in dissolution seams and stylolites. solution structures, with infillings showing a character of a solution residuum. Processes of pressure-solution and chemical compaction have strongly affected MATERIAL AND METHODS the sedimentary successions of the High-Tatric series, leading to the substantial thickness reduction of some Due to the great variability of both shapes and re- lithosomes (Łuczyński 2001b), and also altered the in- lations to the bedding planes, all described structures 560 PIOTR ŁUCZYŃSKI AND ANNA JEZIERSKA

Text-fig. 4. Outcrop area of the Dudziniec Formation in the Kościeliska Valley (after Bac-Moszaszwili et al. 1979) and location of the studied sections with neptunian dykes

filled with internal sediments and calcite cements are synsedimentary tectonics on the development of the further termed as dykes, irrespective of their orienta- area was made. The description of the sections and tion, and the interconnected networks of dykes are re- their correlation, as well as the facies distinguished ferred to as a system of dykes. Due to the interpreted and the microfacies of the host rocks are adapted marine origin of the infilling deposits (see below) the after Jezierska et al. (1916). Due to the mixed carbon- term “neptunian dykes” is used throughout the paper, ate-clastic character of these deposits a combination and not the broader term “sedimentary dykes”. of different classifications (Dunham 1962; Pettijohn The studied systems of dykes and associated et al. 1972; Zuffa 1980) had to be applied to describe structures filled with sediments and hosted by the particular microfacies. Dudziniec Formation outcrop in the Kościeliska The lithology and internal sedimentary structures Valley in the Western Tatra Mountains (Text-fig. 4). of the sediments infilling the voids have been studied The Lower Jurassic deposits hosting the described in detail. The relation of internal sediments to the ce- structures occur on both sides of the Kościeliski ments occurring in the voids was also analyzed. Thirty Stream, between the Raptawicka Turnia crest and the thin sections were made from samples of characteristic Wąwóz Kraków gorge on the north, and the Smytnia sediments, cements or sedimentary structures. Valley on the south. The natural exposures are generally small and scattered, and due to the location of the area in the Tatra National Park, no artificial ex- RESULTS cavations could be carried out. Therefore, particular structures can be observed only on limited surfaces, Distribution of the neptunian dykes and and their overall architecture on a bigger scale cannot stratigraphy of the host rocks be determined. The best developed and well exposed systems of dykes occur in the localities, in which The dykes occur in profiles 1 to 3, exposed in sections 1, 2 and 3 of Jezierska et al. (2016) were de- which are the lower parts of the Dudziniec Formation scribed (Text-fig. 5), or close to them. outcropping in the Kościeliska Valley (Text-figs 4 and The general visible shapes of the systems of dykes, 5). They are hosted by pinkish-grey/pinkish-white the character of their walls and the relation of the in- hybridic limestones of Facies I (Text-fig. 6A), mi- filling sediments to the host-rocks have been studied. crofacially represented by sparry-hybridic arenites The position of the dykes within the sections of the (Text-fig. 6B; for a detailed facies and microfacies de- Dudziniec Formation was analysed, and an eventual scription of the studied sections see Jezierska et al. correlation of their existence with particular facies 2016), and by pinkish-purple sandy-conglomeratic and/or other structures that point to the influence of limestones of Facies II (Text-fig. 6C), microfacially NEPTUNIAN DYKES IN THE DUDZINIEC FORMATION, POLISH TATRA MOUNTAINS 561

Facies Lithology section 5 Facies VII massive limestones (Raptawicka Turnia Formation) Facies VI crinoidal sandstones 50

Facies V crinoidal limestones section 4 46 sandy conglomeratic Facies IV limestones 44 section 6 44 Facies III sandy limestones 32 40 Facies II conglomeratic sandstones 40 28 Dudziniec Formation Facies I sandstones 36 36 24 neptunian dykes section3 32 32 20 section 2 28 section 1 16 28 16 12 24 12 12 24 12 8 20 8 8 20 8 4 16 4 4 16 4 0 12 0 0 12 0 8 8

4 4 0 0

Text-fig. 5. Sections of the Dudziniec Formation in the Kościeliska Valley (after Jezierska et al. 2016), with the position of the studied neptunian dykes

represented by silicidoloclastic-bioclastic wackestones are overlain by Facies III, developed as dark-grey san- (Text-fig. 6D). As far as the exposures permit one to dy-conglomeratic limestones (silicidoloclastic-bioclas- study their distribution in detail, the dykes are evenly tic packstones) in section 3, which correspond well distributed within these two facies and do not follow to the “grey to dark grey and black limestones” of any particular horizons. The summarised thickness the Smytnia Member of Lefeld et al. (1985) of late of the two facies in the studied sections is around 12 Sinemurian to early Pliensbachian age. m. No dykes have been found higher in the sections, and no internal unconformity or discontinuity surface General shapes, dimensions and relation within the Dudziniec Formation, from which the dykes to the host-rocks would penetrate downwards, has been identified. The internal stratigraphy of the Dudziniec For- The rocks hosting the neptunian dykes are usually mation is still poorly understood. Local correlation indistinctly bedded (Text-fig. 6A). In Facies I the beds of the sections in the Kościeliska Valley, based on are typically 30−100 cm thick, in Facies II – 10−30 geometrical relations, facies and microfacies, has been cm thick. The dykes run irregularly in all directions proposed by Staśkiewicz (2015) and by Jezierska et al. in relation to the bedding – along the bedding planes (2016). The conglomeratic limestones of Facies II in or parallel to them, but they also cut them perpen- sections 2 and 3 contain fairly abundant, but mostly dicularly and obliquely (Text-fig. 7A−C). In contrast poorly preserved brachiopod and bivalve faunas. to the Triassic hosting the Middle Jurassic dykes in The occurrence of Spiriferina [Spiriferina walcotti the foldic and parautochthonous units, the bedding Sowerby, 1822 or Dispiriferina davidsoni (Eudes-Des- planes in the Dudziniec Formation are poorly devel- longschamps, 1865)] in Facies II in section 2 indicates oped, and usually cannot be traced for long distances its Sinemurian to Early Pliensbachian age (Siblik 1965; laterally, and therefore they are only rarely followed Rousselle 1977). Most probably, Facies I and II corre- by the dykes. spond to Unit 1 (complex 1) of Horwitz and Rabowski The described dykes show a whole array of ir- (1922), who determined its age as Sinemurian. They regular shapes (Text-fig. 7). The width is variable, 562 PIOTR ŁUCZYŃSKI AND ANNA JEZIERSKA

Text-fig. 6. Facies and microfacies of the Dudziniec Formation hosting the described neptunian dykes. A, B – Facies I, section 1; hybridic limestones (A), sparry-hybridic arenites (B); C, D – Facies II, section 2; sandy-conglomeratic limestones (C), silicidoloclastic-bioclastic wackestones (D); E – intraformational breccia composed of semi-lithified clasts, section 4

usually between few and a dozen or so centimetres, dykes filled with various sediments and cements that and commonly differs within a single structure (Text- it has an appearance of an internal breccia (Text-fig. fig. 7A). Only rarely do the dykes follow any partic- 7E, F). The nests of such internal breccias have irregular orientation or relation to the bedding planes on ular shapes, with no distinct elongations, and their distances longer that a metre. The ramifications are dimensions, as seen in cross-cuts on the exposed sur- usually short and irregular. In several places the host- faces, do not exceed few square metres, usually less rock is so densely cut by a network of cross-cutting than a square metre. NEPTUNIAN DYKES IN THE DUDZINIEC FORMATION, POLISH TATRA MOUNTAINS 563

Text-fig. 7. Neptunian dykes penetrating the Dudziniec Formation. A – system of mainly vertical dykes filled with orange sandstones accompanied by calcite cements; section 2; B – dyke filled with red pelitic material; section 3; C – network of dykes running in various directions in relation to the bedding; section 3; D – irregularly shaped dykes filled with red pelitic material and calcite cements; section 1; E, F – internal breccias; section 3

Infillings violet calcilutites of Microfacies A (Text-fig. 8A). The micritic and microsparry material is usually ar- The neptunian dykes penetrating the Dudziniec ranged in laminae subtly differing in fraction and Formation are filled with various types of deposits colour. The colour differences are most probably re- and cements. lated to the varied content of dispersed ferruginous Most commonly the dykes are filled with var- compounds. The lamination generally runs parallel iously coloured pelitic limestones – usually red to to the walls of the dykes (which in variously oriented orange, but less commonly also white, grey, pink and structures corresponds to horizontal, vertical and 564 PIOTR ŁUCZYŃSKI AND ANNA JEZIERSKA

Text-fig. 8. Microfacies of the infillings of the neptunian dykes. A – calcilutites (Microfacies A); section 3; B – small corroded quartz grain (Q) embedded in variously coloured calcilutites (c, d) of Microfacies A (from Staśkiewicz 2015); section 2; C, D – fine calcarenites of Microfacies B with strongly corroded fragments of possible crinoid origin; section 2; E – ferruginous hybridic arenites of Microfacies C; section 1; F – stylolitic contact between calcilutites (Microfacies A) infilling the dyke and the host rock; section 3

oblique lamination as related to the host-rocks’ bed- walls, the calcilutites, which are generally devoid of ding). Only in the nests with internal breccia in some any coarser material, contain small (up to 0.6 mm in places does it show a more complex character, with diameter) corroded quartz grains (Text-fig. 8B). cross beddings and internal erosional surfaces. In Fine calcarenites (Microfacies B), are the second some cases, the pelitic material is separated from the sediment commonly present in the dykes (Text-fig. host rocks by a zone of calcite cements (Text-fig. 7D). 8C, D). Macroscopically they are usually indiscern- Sporadically, mainly in the laminae neighbouring the ible from the pelitic limestones described above; NEPTUNIAN DYKES IN THE DUDZINIEC FORMATION, POLISH TATRA MOUNTAINS 565 however in this case the material is composed of in the dykes, both as individual grains, and as larger carbonate grains with dimensions typically ranging rock fragments. The walls are often corroded, and the between 0.1 and 0.5 mm, occasionally larger. Some finer internal sediment penetrates between the larger of the grains can be identified as strongly corroded clasts of the host-rock, which, taking into account the crinoid ossicles. The calcarenites are usually orange small contrast between the two lithologies, results to red in colour (due to staining by dispersed ferru- in the gradual character of the transition between ginous compounds). In a similar fashion to the calci- the surrounding rock and the dyke’s infilling. Calcite lutites, they occur in all types of structures (vertical, cements covering the walls are very rare. horizontal, etc.), form laminae and occasionally are In places in which the rocks are densely cut by accompanied by layers of calcite cements. variously oriented dykes, the occurrence of large, The third distinct type of sediments filling the sharp-edged fragments of the host-rock in a para in dykes are red, ferruginous calcareous sandstones, situ position, give the structures an appearance of an microfacially represented by ferruginous hybridic internal breccia. arenites – Microfacies C (Text-fig. 8E). The arenites are composed of quartz grains (up to 50% of the rock volume), accompanied by alkaline feldspars (5%) and DISCUSSION by dolomicritic and dolomicrosparitic grains (up to 10%), in a sparry or pseudosparry matrix. Rare cor- In the Central Western Carpathians, the Lower roded crinoidal elements and shell fragments are also and Middle Jurassic sequences record the great in- present. The grain elements are poorly sorted, with fluence of synsedimentary tectonic activity on the dimensions ranging typically between 0.5 and 2 mm area’s development. As a result of the opening of (individual quartz grains reaching up to 8 mm). the Vahic Ocean, the Carpathian region became In many cases different types of infillings co-oc- separated from the stable continent of Palaeoeurope cur in particular systems of interconnected dykes, (Plašienka et al. 1997; Csontos and Vörös 2004). Vast although individual structures filled by only one par- carbonate platforms that developed in the Triassic ticular type of internal deposit can also be found. were subjected to disintegration due to a prevailing Generally, microfacies A and B (calcilutites and cal- extensional regime (Plašienka 1995, 2012; Michalík carenites) occur together in broader dykes (or broader 2007). These processes were commonly accompa- parts of dykes), where they form laminae, commonly nied by the development of neptunian dykes hosted accompanied by calcite cements. Narrower and more by the Triassic and Jurassic rocks and filled with distant ramifications are usually filled by calcilutites Jurassic sediments. In the CWC, apart from the Tatra and/or calcite cements. Sandstone infillings occur in Mts., the Jurassic neptunian dykes are known mainly separate systems, but can also be found accompa- from the Pieniny Klippen Belt (Zydorowicz 1991; nying other types of internal deposits, mainly in the Mišik 1994; Aubrecht and Kozur 1995; Mišik et al. nests of internal breccias. 1995; Aubrecht and Túnyi 2001; Sidorczuk 2005; Wierzbowski et al. 2005; Schlögl et al. 2009). Lower Character of walls Jurassic neptunian dykes and associated breccias are recorded also from other areas of the Alpine system, The character of the walls of dykes largely de- such as: Male Karpaty (Michalík et al. 1994), Julian pends on the type of the infilling deposits, as well as Alps (Črne et al. 2007), southern Alps (Winterer et on their architecture. In the case of dykes filled with al. 1991) and Spain (Winterer and Sarti 1994). fine calcareous material (microfacies A and B), in Syndepositional tectonic instability influenced which there is a distinct contrast between the internal the sedimentary development during the Early and sediment and the host-rocks, the contact is sharp, Middle Jurassic in both the High-Tatric and the Sub- although usually irregular and overprinted by styloli- Tatric domains (Jach 2002, 2005; Łuczyński 2002). tisation (Text-fig. 8F). Individual quartz grains, most In the High-Tatric area it governed the facies devel- probably derived from the host-rocks, occur in places opment, their distribution, as well as the complete- embedded in the micritic material infilling the dykes, ness of the stratigraphic record (Wieczorek 2000; mostly in vertical structures. In some cases the walls Jezierska and Łuczyński 2016). The occurrence of are covered by calcite cements. neptunian dykes is commonly one of the important The walls of the dykes filled with calcareous sand- symptoms of such activity. Yet, almost no neptu- stones (Microfacies C) are very ragged and irregular. nian dykes have been described so far from the thick Common are elements of the host-rocks embedded Lower Jurassic Dudziniec Formation exposed in the 566 PIOTR ŁUCZYŃSKI AND ANNA JEZIERSKA autochthonous unit, the sedimentary record of which dykes clearly penetrate downwards from an uncon- indicates great influence of syndepositional tectonic formity surface located at the base of the formation, activity on the facies development. The deposition of and the length of narrow fissures, often cutting the mixed sandy-carbonate facies was controlled mainly substrate to depths exceeding 100 m, made such an by tectonic activity and by the distance from alimen- interpretation plausible. In the studied case, with no tation areas, with the sandy facies representing peri- dykes found higher in the sections of the Dudziniec ods of block faulting and instability, and the crinoidal Formation, it seems very unlikely that the fine car- facies corresponding to the episodes of deposition in bonate material could have been derived from car- relatively stable conditions (K. Wójcik 1979, 1981; bonate sediments of the Middle Jurassic. Staśkiewicz 2015; Jezierska et al. 2016). The fine calcarenites (Microfacies B) contain fine So far from the High-Tatric succession have been and strongly corroded carbonate grains identified as recorded mainly neptunian dykes penetrating the crinoid ossicles, and the calcilutites (Microfacies A) Triassic and filled by the Middle Jurassic deposits very fine corroded quartz grains (Text-fig. 8B). It is (Łuczyński 2001a) best developed in the allochtho- very difficult to envisage the source of this mate- nous Czerwone Wierchy and Giewont units. Dykes rial. Potentially it could be derived from the walls of filled with the Dudziniec Formation were described the fissures, as both crinoidal and sandy facies are by Radwański (1959b) from the Smytnia valley, present in the sedimentary column that is cut by the whereas dykes hosted by the same formation (its dykes. However, their dimensions and size segrega- topmost part) were mentioned by Bagiński (1985) tion, as well as the corrosion of their surfaces, indi- from the parautochthonous folds of the Rzędy pod cate that they have undergone substantial transport, Ciemniakiem area. In the present paper dykes are and were subjected to weathering. This suggest that discussed that penetrate the lower parts of the for- they come from an external source. mation in the autochthonous series. Their occurrence Radwański (1959b) describing the dykes filled corresponds well to the general picture of facies de- with Lower Jurassic material and penetrating the velopment of the area in the Early Jurassic. Norian in the Smytnia Valley pointed out that they are infilled by calcareous quartz-dolomite sand- Origin of the infilling sediments and character stones, identical to the overlying Liassic, but also, of deposition within the voids particularly in the more remote parts of the voids, by yellow dolomitic marls, the source of which is The studied systems of neptunian dykes are in- difficult to determine. He attributed their occurrence filled by two distinct types of deposits (fine carbon- partly to sieving, but also suggested that the mate- ates of Microfacies A and B, and coarse-grained rial was partly dissolved and reprecipitated in the sandstones of Microfacies C), and although some- dykes. In that case exposed parts of Norian lime- times they co-occur in the same interconnected net- stones were dissolved. A similar process can explain works, the two varieties of internal sediments must the occurrence of calcilutites and fine calcarenites of have been derived from different sources and depos- Microfacies A and B in the dykes described herein. ited in a different manner. In the Early Jurassic, during the deposition of The calcilutites and fine calcarenites of the Dudziniec Formation, the Czerwone Wierchy and Microfacies A and B have no counterparts in the Giewont units were uplifted and exposed to subaer- sedimentary column of the Dudziniec Formation, ial weathering (Łuczyński 2002). In those areas, the which could facilitate as their source rocks. The Middle Jurassic rests directly on Triassic (Anisian) occurrence of very fine, often ferruginous pelitic limestones. Subjected to erosion were mainly the material devoid of microfossils in vast systems of Triassic limestones and dolomites of the foldic units, neptunian dykes is often attributed to the so-called however, due to block faulting, probably some parts “sieve effect” (Wiedenmayer 1964; Winterer et al. of the autochthonous unit, in which sedimentation 1991) with very fine particles percolating down into of sandy-crinoidal facies took place, also became the interconnected networks. Such an interpretation temporarily uplifted and eroded. In the parautoch- was proposed for the vast systems of dykes filled thonous series in the Rzędy pod Ciemniakiem area, with red pelite and hosted by the Triassic of the High- the Dudziniec Formation is limited to a thickness of Tatric series (Łuczyński 2001a). In that case, the red a few up to a dozen or so metres, or is even missing crinoidal limestones of the Bathonian Krupianka in some sections (Łuczyński 2002; Jezierski 2014). It Formation were interpreted to be the source of the in- cannot be also excluded that, due to differentiation of filling material. However, in that case the systems of the sea bottom caused by syndepositional tectonic ac- NEPTUNIAN DYKES IN THE DUDZINIEC FORMATION, POLISH TATRA MOUNTAINS 567 tivity, small isolated carbonate platforms developed any case, the age of a neptunian dyke is determined within the autochthonous domain, which acted as by the age of the infilling deposits. alimentation areas. If the above presented conclusions concerning The products of weathering were washed by sur- the nature and the source of the deposits filling the face waters, probably mainly after heavy rains, into described structures are correct, the dykes are in- the sedimentary basin of the autochthonous unit, traformational, and their whole development his- partly as small suspended particles and partly dis- tory marks a distinct and probably a relatively short solved, finally reaching the fissures open on the sea episode following the deposition of Facies II. The bottom. Reprecipitation of dissolved ions resulted in lack of dykes penetrating the deposits of Facies III development of microsparry infillings. Larger par- and younger suggests that this episode terminated ticles washed into the fissures are represented by before their deposition. This indicates that the age corroded crinoidal elements and small quartz grains, of the dykes is most probably Sinemurian to early probably derived mainly from the uplifted parts of Pliensbachian. However, it cannot be entirely ex- the parautochthonous areas. Final determination of cluded that the systems cut also the younger deposits the nature of these deposits requires further detailed of Facies III or even IV, but their higher parts – mas- petrological and geochemical studies. ter dykes (see Mallarino 2002), are not exposed and Both facially and microfacially the ferruginous simply have not been found. This may be suggested calcareous sandstones (ferruginous hybridic aren- by the lithological resemblance of the ferruginous ites of Microfacies C) infilling the dykes resemble calcareous sandstones infilling the dykes and the cal- the sandstone facies components of the Dudziniec careous lithic sandstones of Facies IV in the sections. Formation outcropping in the Kościeliska Valley. This In this case, the sediments of Facies IV would be suggests that this type of dyke is intraformational, the source rock of the sandstone infillings, and the and that the source of their infillings should be sought age of the dykes would be accordingly younger. A within the Lower Jurassic sequences. The closest re- younger – late Pliensbachian age of the dykes would semblance is to the pinkish-grey/pinkish-white hy- be in accordance with the syndepositional tectonic bridic sandstones of Facies I, outcropping in sections activity in the Sub-Tatric Križna Unit, marked by the 1 to 3 (see Jezierska et al. 2016). However, in sections appearance of crinoidal facies (Jach 2002). 2 and 3 the dykes with these deposits are hosted by Fracturing of the host rocks indicates that they the overlying Facies II (Text-fig. 6), which indicates must have been relatively quickly sufficiently lith- that the material must have been derived from a dif- ified (Masse et al. 1998). Rapid lithification is char- ferent, younger source. Potentially the sandy material acteristic rather for e.g., microbial carbonates or could also come from calcareous lithic sandstones beach rocks and not for grainstone facies (de Wet et of Facies IV, siliceous conglomeratic sublithic-sub- al. 1999). Most probably, early lithification of at least arkose sandstones of Facies V, or even hybridic cri- some parts of the Dudziniec Formation sequence noidal sandstones of Facies VII. However, no dykes was possible due to temporary subaerial exposure of have been found hosted by rocks higher in the sections the sediments and the influence of meteoric waters than Facies II, which makes this hypothesis doubtful. during early diagenesis (compare Dravis 1996). The Therefore, most probably the ferruginous calcareous coarse-grained facies (e.g., Facies II in section 4) con- sandstones that infill the dykes are derived from fa- tain internal erosional surfaces and intraformational cies that are absent in the sections exposed in the breccias composed of semi-lithified clasts (Text-fig. Kościeliska Valley in direct vicinity of the described 7E; Staśkiewicz 2015; Jezierska et al. 2016) and thus structures. At least part of the material could come probably the sequence abounds in hidden, unrecog- also directly from the walls of the dykes. nisable associated sedimentary gaps. It is characteristic that the dykes are found in the eastern area of Age of the dykes, initiation and development exposure of the Dudziniec Formation (Kościeliska of voids Valley), in shallow-most facies, and are not found in the west (Chochołowska Valley) representing the The history of dykes filled with sediments, such deeper parts of the basin. On the other hand, the as neptunian dykes, is often separated into three ragged surfaces of the walls of the dykes, particularly stages: initiation, development and infilling (Smart those filled with sandstones, indicate that the host- et al. 1987). Particular stages can be short and occur rocks were not fully lithified. directly one after another, or even simultaneously, or The development of the discussed structures took can be separated by a considerable amount of time. In place in multiple stages. The irregularity of the voids 568 PIOTR ŁUCZYŃSKI AND ANNA JEZIERSKA and fissures hosting the internal sediments, and the present on the sea bottom at the time of fracturing. occurrence of internal breccia nests, indicate that The fine carbonate internal deposits most probably their initiation and development processes cannot be came from uplifted and corroded carbonate massifs attributed to a single fracturing event. The same can (possibly from the allochthonous High-Tatric units). be stated about the infilling processes, as is indicated Products of weathering, both in dissolved form and by the complex architecture of the infilling deposits, as small particles, were washed into the sedimen- with laminations, internal erosional surfaces and the tary basin of the autochthonous unit, and redeposited occurrence of layers of calcite cements (compare e.g., within the dykes. Blendinger 1986). During the periods in which the 6) The early ideas of the late Professor Andrzej systems of interconnected voids and fissures became Radwański, to whom this issue is dedicated, partic- sealed and were not permeable for deposits, calcite ularly those concerning the origin of fine carbonate cements precipitated in the remaining spaces. material filling the dykes, are still inspiring and can The time relation between the infilling of the explain the sedimentary phenomena described here dykes by fine carbonate sediments of Microfacies very well. A and B and by the sandstones of Microfacies C is unclear, as no univocal cross-cutting relations are visible. The two types of deposits co-occur in some Acknowledgements of the structures, which suggests that the processes of their deposition, in both cases taking place in several The authors thank the authorities of the Tatra National Park stages, generally represent the same episode of for- for permission to conduct fieldwork and to collect samples. We mation of neptunian dykes. also wish to express our gratitude to journal reviewers – Jozef Michalík and Renata Jach, who commented on the manuscript and thus helped to improve its final version. CONCLUSIONS

The studies of neptunian dykes penetrating the REFERENCES Lower Jurassic Dudziniec Formation exposed in the Kościeliska Valley in the High-Tatric succession of Andrusov, D., Bystricky, J. and Fusan, O. 1973. Outline of the the Tatra Mountains allow us to present the following structure of the Western Carpathians, 1–44. Guide-book general conclusions: for the geological excursion, X Congress of the Carpath- 1) The sedimentary development of the Lower ian-Balkan Geological Association. Bratislava. Jurassic sandy-carbonate facies in the autochthonous Aubrecht, R. and Kozur, H. 1995. Pokornyopsis (Ostracoda) unit, as was previously postulated, was strongly in- from submarine fissure fillings and cavities in the Late fluenced by synsedimentary tectonic activity, such as Jurassic of Czorsztyn Unit and the possible origin of the block-faulting. The described dykes are yet another recent anchialine fauna. Neues Jahrbuch für Geologie und symptom of these processes. Paläontologie, Abhandlungen, 196, 1–17. 2) The distribution of Jurassic neptunian dykes Aubrecht, R. and Túnyi, I. 2001. Original orientation of neptu- in the High-Tatric succession is limited neither to the nian dykes in the Pieniny Klippen Belt (Western Carpath- foldic and parautochthonous units nor to the Triassic ians): the first results. Contributions to Geophysics and as the host rocks. The relatively rare occurrence of Geodesy, 31, 557−578. dykes in the Dudziniec Formation of the autochtho- Bac-Moszaszwili, M., Burchart, J., Iwanow, A., Jaroszewski, nous unit is probably caused by different mechani- W., Kotański, Z., Lefeld, J., Mastella, L., Ozimkowski, W., cal properties of the poorly bedded coarse-grained Roniewicz, P., Skupiński, A. and Westwalewicz-Mogilska, sandy crinoidal rocks as compared to the well-bed- E. 1979. Geological map of the Polish Tatra Mts. at the ded Triassic limestones and dolomites. scale of 1:30 000. Wydawnictwa Geolologiczne; Warsza- 3) The described dykes are most probably of wa. [In Polish] Sinemurian to Pliensbachian age. Bagiński, S. 1985. High-Tatric Jurassic in the Rzędy pod Ciem- 4) The development of the fissures took place in niakiem area, Tatra Mountains. Unpublished Msc Thesis, multiple stages and the infilling deposits came from Jagiellonian University, Cracow. [In Polish] multiple sources. The same fractures opened several Blendinger, W. 1986. Isolated stationary carbonate platforms: times. the Middle Triassic (Ladinian) of the Marmolada area, Do- 5) The sandy varieties of the infillings came di- lomites, Italy. Sedimentology, 33, 159–184. rectly from the host rocks or from loose sediments Črne, A., Šmuc, A. and Skaberne, D. 2007. Jurassic neptunian NEPTUNIAN DYKES IN THE DUDZINIEC FORMATION, POLISH TATRA MOUNTAINS 569

dikes at Mt Mangart (Julian Alps, NW Slovenia). Facies, Kotański, Z. 1979. The position of the Tatra Mts in the Western 53, 249−265. Carpathians. Przegląd Geologiczny, 27, 359–369. [In Polish] Csontos, L. and Vörös, A. 2004. Mesozoic plate tectonic re- Lefeld, J., Gaździcki, J., Iwanow, A., Krajewski, K. and Wójcik, construction of the Carpathians region. Palaeogeography, K. 1985. Jurassic and Cretaceous lithostratigraphic units of Palaeoclimatology, Palaeoecology, 210, 1–56. the Tatra Mountains. Studia Geologica Polonica, 84, 1–93. de Wet, C., Dickson, J., Wood, R., Gaswirth, S. and Frey, H. Lehner, B. 1991. Neptunian dykes along a drowned carbonate 1999. A new type of shelf margin deposit: rigid microbial platform margin: an indication of recurrent extensional tec- sheets and unconsolidated grainstones riddled with meter tonic activity? Terra Nova, 3, 593–602. scale cavities. Sedimentary Geology, 128, 13–21. Łuczyński, P. 2001a. Development history of Middle Jurassic Dravis, J. 1996. Rapidity of freshwater calcite cementation – neptunian dykes in the High-Tatric series, Tatra Mountains, implications for carbonate diagenesis and sequence stratig- Poland. Acta Geologica Polonica, 51, 237–252. raphy. Sedimentary Geology, 107, 1–10. Łuczyński, P. 2001b. Pressure-solution and chemical compac- Dunham, R. 1962. Classification of carbonate rocks according tion of condensed Middle Jurassic deposits, High-Tatric se- to depositional texture. AAPG Memoir, 1, 108–121. ries, Tatra Mountains. Geologica Carpathica, 52, 91–102. Eudes-Deslongschamps, E. 1865. Recherches sur l’organisation Łuczyński, P. 2002. Depositional evolution of the Middle Ju- du manteau chez les Brachiopodes articulés et principale- rassic carbonate sediments in the High Tatric succession, ment sur les spicules calcaires contenus dans son interieur. Tatra Mountains, Western Carpathians, Poland. Acta Geo- Mémoires de la Société Linnénne de Normandie, 14, 1–36. logica Polonica, 52, 265–378. Horwitz, L. and Rabowski, F. 1922. Sur le Lias et le Dogger Mallarino, G. 2002. Piana Degli Albanesi, Monte Kumeta hauttatriques de la Tatra. Posiedzenia Naukowe Państwo- and the “Saccense Domain”: pelagic resedimented, and wego Instytutu Geologicznego, 3, 15–18. [In Polish with high-energy skeletal post-drowning facies from western French summary] Sicily. Appendix – neptunian dykes at Monte Kumeta. In: Jach, R. 2002. Lower Jurassic spiculite series from the Križna M. Santantonio (Ed.), 6th International Symposium on the Unit in the Western Tatra Mts, Western Carpathians, Poland. Jurassic System. Palermo, Italy, 12−22 September 2002. Annales Societatis Geologorum Poloniae, 72, 131–144. General Field Trip Guidebook, pp. 205–209. Palermo. Jach, R. 2005. Storm-dominated deposition of the Lower Juras- Masse, J-P., Borgomano, J. and Al Maskiry, S. 1998. A platform sic crinoidal limestones in the Križna unit, Western Tatra transition for lower Aptian carbonates (Shuaiba Formation) Mountains, Poland. Facies, 50, 561–572. of the northeastern Jebel Akhdar (Sultanate of Oman). Sed- Jenkyns, H. 1971. The genesis of condensed sequences in the imentary Geology, 119, 297–309. Tethyan Jurassic. Lethaia, 4, 327–352. Matyszkiewicz, J., Krajewski, M., Kochman, A., Kozłowski, Jezierska, A. and Łuczyński, P. 2016. Jurassic unconformities A. and Duliński, M. 2016. Oxfordian neptunian dykes with in the High-Tatric succession, Tatra Mountains, Poland. brachiopods from the southern part of the Kraków-Często- Geological Quarterly, 60, 273–290. chowa Upland (southern Poland) and their links to hydro- Jezierska, A., Łuczyński, P. and Staśkiewicz, A. 2016. Carbon- thermal vents. Facies, 62, 12. ate-clastic sediments of the Dudziniec Formation (Lower Michalík, J. 2007. Sedimentary rock record and microfacies in- Jurassic) in the Kościeliska Valley (High-Tatric series, dicators of the latest Triassic to mid-Cretaceous tensional Tatra Mountains, Poland): role of syndepositional tectonic development of the Zliechov Basin (Central Western Car- activity during the Early and Middle Jurassic. Geological pathians ). Geologica Carpathica, 58, 443–453. Quarterly, 60, 869–880. Michalík, J., Rehakova, D. and Sotak, J. 1994. Environments Jezierski, P. 2014. Character of the unconformity between the and setting of the Jurassic Lower Cretaceous succession in Triassic and the Jurassic in the autochthonous unit of the the Tatric area, Male Karpaty Mts. Geologica Carpathica, Tatra Mountains. Unpublished Msc Thesis, University of 45, 45–56. Warsaw. [In Polish] Mišík, M. 1994. The Czorsztyn Submarine Ridge (Jurassic − Jones, B. 1992. Void-filling deposits in karst terrains of isolated Lower Cretaceous, Pieniny Klippen Belt): an example of oceanic islands: a case study from Tertiary carbonates of a pelagic swell. Mitteilungen der Österreichischen Geolo- the Cayman Islands. Sedimentology, 39, 857–876. gischen Gesellschaft, 86, 133–140. Jurewicz, E. 2005. Geodynamic evolution of the Tatra Mts. and Mišik, M., Sykora, M., Siblik, M. and Aubrecht, R. 1995. Sed- the Pieniny Klippen Belt (Western Carpathians): problem imentology and brachiopods of the Lower Jurassic Luty and comments. Acta Geologica Polonica, 55, 295–338. Potok limestone (Slovakia, West-Carpathian Klippen belt). Jurewicz, E. 2012. Nappe-thrusting processes in the Tatra Mts. Geologica Carpathica, 46, 41–51. Przegląd Geologiczny, 60, 432–451. [In Polish with En- Pettijohn, F., Potter, P. and Siever, R. 1972. Sand and Sand- glish summary] stones, 1–618. Springer; New York. Kotański, Z. 1959. Stratigraphic sections of the High-Tatric Plašienka, D. 1995. Passive and active margin of the northern Series in the Polish Tatra Mts. Biuletyn Instytutu Geolog- Tatricum (Western Carpathians, Slovakia). Geologische icznego, 139, 7–160. [In Polish] Rundschau, 84, 748–760. 570 PIOTR ŁUCZYŃSKI AND ANNA JEZIERSKA

Plašienka, D. 2012. Jurassic syn-rift and Cretaceous syn-orogen- Staśkiewicz, A. 2015. Lower Jurassic (Dudziniec Formation) ic, coarse-grained deposits related to opening and closure of in the Kościeliska Valley (Tatra Mts.). Unpublished Msc the Vahic (South Penninic) Ocean in the Western Carpathi- Thesis, University of Warsaw. [In Polish] ans – an overview. Geological Quarterly, 56, 601–628. Uchman, A. 2014. Introduction – sedimentary rocks of the Ta- Plašienka, D., Grecula, P., Putiš, M., Kováč, M. and Hovorka, tra Mountains. In: R. Jach, T. Rychliński and A. Uchman D. 1997. Evolution and structure of the Western Carpathi- (Eds), Sedimentary Rocks of the Tatra Mountains, 12−28. ans: an overview. Mineralia Slovaca – Monograph, 67–72. Wydawnictwa Tatrzańskiego Parku Narodowego; Zako- Rabowski, F. 1954. Researches in the Kominy Tylkowe region pane. in the Tatra Mountains performed in 1938. Biuletyn Insty- Wendt, J. 1971. Genese und Fauna submariner sedimentärer tutu Geologicznego, 86, 29–35. [In Polish] Spaltefüllungen im mediterranen Jura. Palaeontographica Rabowski, F. 1959. High-Tatric series in western Tatra. Prace Abhandlungen A, 136, 122–192. Instytutu Geologicznego, 27, 1–173. [In Polish] Wendt, J. 2017. A unique fossil record from neptunian sills: the Radwański, A. 1959a. Researches on petrography of the world’s most extreme example of stratigraphic condensa- High-Tatric Lias. Przegląd Geologiczny, 7, 359–362. [In tion (Jurassic, western Sicily). Acta Geologica Polonica, Polish] 67, 163–199. Radwański, A. 1959b. Littoral structures (cliff, clastic dikes Wieczorek, J. 2000. Condensed horizons as turning events in and veins, and borings of Potamilla in the High-Tatric Lias. passive margin evolution: The Tatra Mts. examples. Zen- Acta Geologica Polonica, 9, 31–280. [In Polish with En- tralblatt für Geologie und Paläontologie, Teil I, Jahrgang glish summary] 2000, 1/2, 199–209. Radwański, A. 1968. Petrographical and sedimentological Wiedenmayer, F. 1964. Obere Trias bis mittlerer Lias zwischen studies of the High-Tatric Rhaetic in the Tatra Mountains. Saltrio und Tremona (Lombardische Alpen). Die Wechsel- Studia Geologica Polonica, 25, 1–146. [In Polish with En- beziehungen zwischen Stratigraphie, Sedimentologie und glish summary] syngenetischer Tektonik. Eclogae Geologicae Helvetiae, Rousselle, L. 1977. Spiriférines du Lias moyen et supérieur 56, 529–640. au Maroc (Rides Prérifaines; Moyen Atlas) et en Es- Wierzbowski, A., Schlögl, J., Aubrecht, R. and Krobicki, M. pagne (Chaine Celtibérique orientale). Notes du Service 2005. Rediscovery of the classic locality of Callovian in geologique du Maroc, 38, 153–175. Babiarzowa Klippe (Pieniny Klippen Belt, Poland). Tomy Schlögl, J., Mangold, C., Tomašových, A. and Golej, M. 2009. Jurajskie, 3, 11–14. Early and Middle Callovian ammonites from the Pieniny Winterer, E., Metzler, C. and Sarti, M. 1991. Neptunian dykes Klippen Belt (Western Carpathians) in hiatal successions: and associated breccias (Southern Alps, Italy and Switzer- unique biostratigraphic evidence from sediment-filled fis- land): role of gravity sliding in open and closed systems. sure deposits. Neues Jahrbuch für Geologie und Paläontol- Sedimentology, 38, 381–404. ogie, Abhandlungen, 252, 55–79. Winterer, E. and Sarti, M. 1994. Neptunian dykes and associat- Siblik, M. 1965. Some new Liassic brachiopods. Geologický ed features in southern Spain: mechanics of formation and Sborník Slovenskej Akadémie Vied, 16, 1–264. tectonic implications. Sedimentology, 41, 1109–1132. Sidorczuk, M. 2005. Middle Jurassic Ammonitico Rosso depos- Wójcik, K. 1979. Sedimentation and facies development of the its in the northwestern part of the Pieniny Klippen Belt in High-Tatric Liassic in the Chochołowska Valley. Unpub- Poland and their palaeogeographic importance; A case study lished Msc Thesis, University of Warsaw. [In Polish] from Stankowa Skała and “Wapiennik” quarry in Szaflary. Wójcik, K. 1981. Facies development of the vicinity of the Annales Societatis Geologorum Poloniae, 75, 273–285. Chochołowska Valley. Przegląd Geologiczny, 39, 405– Siemiradzki, J. 1923. Liassic and Jurassic Fauna from the Tatra 410. [In Polish with English summary] Mountains and Podhale. Archiwum Towarzystwa Naukow- Wójcik, Z. 1959. High-Tatric series of the southern slopes of ego we Lwowie, 3, 1–3. [In Polish] Bobrowiec. Acta Geologica Polonica, 9, 165–201. [In Pol- Smart, P.L., Palmer, R.J., Whitaker, F. and Wright, V.P. 1987. ish] Neptunian dykes and fissure fills: an overview and account Zuffa, G. 1980. Hybrid arenites: Their composition and classi- of some modern examples. In: N.P. James and P.W. Cho- fication. Journal of Sedimentary Petrology, 50, 21–29. quette (Eds), Paleokarst, 149–163. Springer Verlag; New Zydorowicz, T. 1991. Diagenesis of the Upper Jurassic pelagic York. deposits of the Pieniny Klippen Belt in Poland. Unpub- Sowerby, J. 1822. The mineral conchology of Great Britain, lished PhD Thesis, Polish Geological Institute. Warszawa 1–383. B. Meredith; London. [In Polish]

Manuscript submitted: 2nd February 2018 Revised version accepted: 14th June 2018